Lowell Hill District

Past Producer in Nevada county in California, United States with commodities Gold, Silver, Platinum

Sections on this page

Identification information
Geographic coordinates
Site location context
Geographic areas
Public Land Survey System information
Commodities
Materials information
Mineral occurrence model information
Host and associated rocks
Nearby scientific data
Geologic structures
Ore body information
Controls for ore emplacement
Economic information about the deposit and operations
Mining district
Land status
Ownership information
Bibliographic references
General comments
Reporter information

Geologic information

Identification information

Deposit ID	10310640
Record type	District
Current site name	Lowell Hill District

Comments on the site identification

The Lowell Hill District is in south-central Nevada County about six miles northeast of Dutch Flat. It includes placer workings in the area of Liberty Hill, Negro Jack Hill, and Remington Hill. The Dutch Flat District lies to the southwest. The district produced more than $1 million from auriferous gravels deposited by a tributary of the ancestral Yuba River.

Geographic coordinates

Geographic coordinates:	-120.77403, 39.25869 (WGS84)
Elevation	1035
Relative position	Six miles northeast of Dutch Flat

Site location context

Political divisions (FIPS codes)

Nevada(county)

California(state)

United States(country)

North America(continent)

Land(continent)

USGS map quadrangles

Washington(quadrangle 1:24,000 scale)

Truckee(quadrangle 1:100,000 scale)

Chico(quadrangle 1:250,000 scale)

Hydrologic units (watersheds)

Upper Bear(hydrologic unit)

Lower Sacramento(hydrologic accounting unit)

Sacramento(hydrologic subregion)

California(hydrologic region)

Geographic areas

Country	State	County
United States	California	Nevada

Public Land Survey System information

Meridian	Township	Range	Section	Fraction	State
Mount Diablo	016N	011E	5-8, 17, 18	.	California
Mount Diablo	017N	011E	31,32		California

Comments on the location information

Location selected for latitude and longitude is the Mammoth Springs Mine portal symbol on the south side of Negro Jack Hill on the USGS 7 1/2-minute Washington quadrangle.

Commodities

Commodity	Importance
Gold	Primary
Silver	Secondary
Platinum Critical	Secondary

Comments on the commodity information

Commodity Info: Upper Gravels at the Liberty Hill workings averaged about $0.24 per cubic yard ($35/oz).

Lower Gravels at the Liberty Hill workings are reported to have ranged between $0.18 and $1.43 per cubic yard ($35/oz).
Ore Materials: Native gold: Fine - coarse gold and nuggets (900 fine)
Gangue Materials: Quartz, metamorphic , and ultramafic gravels and boulders; accessory minerals magnetite, ilmenite, zircon, pyrite, amphibole, epidote, chlorite, and siderite

Materials information

Materials	Type of material
Gold	Ore
Quartz	Gangue
Magnetite	Gangue
Ilmenite	Gangue
Zircon	Gangue
Pyrite	Gangue
Amphibole	Gangue
Epidote	Gangue
Chlorite	Gangue
Siderite	Gangue

Mineral occurrence model information

Model code	119
USGS model code	39a
Deposit model name	Placer Au-PGE
Mark3 model number	54

Host and associated rocks

Host or associated Host

Rock type Unconsolidated Deposit > Sand and Gravel

Stratigraphic age (youngest) Tertiary

Nearby scientific data

(1)	-120.77403, 39.25869	ListMap

Economic information

Geologic structures

Type of structure	Local
Structure description	Melones Fault Zone
Type of structure	Regional
Structure description	Foresthill Fault, Melones Fault Zone

Ore body information

General form Irregular

General form	Irregular

Controls for ore emplacement

Mechanical accumulation on irregular bedrock riffles and within river- and stream-channel lag gravels, bars, and point bar deposits

Comments on the geologic information

REGIONAL SETTING

The northern Sierra Nevada is home to numerous important gold deposits. These include the famous lode districts of Johnsville, Alleghany, Sierra City, Grass Valley, and Nevada City as well as the famous placer districts of North Bloomfield, North Columbia, Cherokee, Foresthill, Michigan Bluff, Gold Run, and Dutch Flat. The geological and historical diversity of most of these deposits and specific mine operations are covered in numerous publications produced over the years by the U.S. Bureau of Mines, U.S. Geological Survey, California Division of Mines and Geology (now California Geological Survey), and others. The most recent geologic mapping covering the area is the 1:250,000-scale Chico Quadrangle compiled by Saucedo and Wagner (1992).

Stratigraphy

The northern Sierra Nevada basement complex has a history of both oceanic and continental margin tectonics recorded in sequences of oceanic, near continental, and continental volcanism. The complex has been divided into four lithotectonic belts: the Western Belt, Central Belt, Feather River Peridotite Belt, and Eastern Belt.

The Western Belt is composed of the Smartville Complex, an Upper Jurassic volcanic-arc complex, which consists of basaltic to intermediate pillow flows overlain by pyroclastic and volcanoclastic rock units with diabase, metagabbro, and gabbro-diorite intrusives. The Cretaceous Great Valley sequence overlies the belt to the west. To the east it is bounded by the Big Bend-Wolf Creek Fault Zone.

East of the Big Bend-Wolf Creek Fault Zone is the Central Belt, which is in turn bounded to the east by the Goodyears Creek Fault. This belt is structurally and stratigraphically complex and consists of Permian-Triassic argillite, slate, chert, ophiolite, and greenstone of marine origin.

The Feather River Peridotite Belt is also fault-bounded, separating the Central Belt from the rocks of the Eastern Belt for almost 95 miles along the northern Sierra Nevada. It consists largely of Devonian-to-Triassic serpentinized peridotite.

The Eastern Belt, or Northern Sierra Terrane, is separated from the Feather River Peridotite Belt by the Melones Fault Zone. The Northern Sierra Terrane is primarily composed of siliciclastic marine metasedimentary rocks of the Lower Paleozoic Shoo Fly Complex overlain by Devonian-to-Jurassic metavolcanic rocks. Farther east are Mesozoic granitic rocks of the Sierra Nevada Batholith.

The northern Sierra Nevada experienced a long period of Cretaceous to early Tertiary erosion followed by extensive late Oligocene to Pliocene volcanism. The oldest Tertiary deposits are Eocene auriferous gravels deposited by the predecessors of the modern Yuba and American rivers and preserved in paleochannels eroded into basement and on adjacent benches. In contrast to earlier volcanism, Tertiary volcanism was continental, with deposits placed on top of the eroded basement rocks, channel deposits, and Mesozoic intrusives. Two regionally important units are the Valley Springs and Mehrten Formations. The Oligocene-Miocene Valley Springs Formation is a widespread unit of intercalated rhyolite tuffs and intervolcanic channel gravels that blanketed and preserved the basal gravels in the valley bottoms. The younger Miocene-Pliocene Mehrten Formation consists largely of andesitic mudflows, which regionally blanketed all but the highest peaks and marked the end of Tertiary volcanism.

Pliocene-Pleistocene uplift of the Sierra Nevada caused the modern drainages to erode through the volcanic Valley Springs-Mehrten sequences and carve deep river gorges into the underlying basement rocks. During this process, the modern rivers became charged with placer-gold deposits from both newly eroded basement rocks and from the reconcentration of the eroded Tertiary placers. The discovery of these modern Quaternary placers in the American River at Sutter's Mill sparked the California Gold Rush.
Tertiary Channel Gravels

It has been estimated that 40 percent of California's gold production has come from placer deposits along the western Sierra Nevada (Clark, 1966). These placer deposits are divisible into Tertiary deposits preserved on the interstream ridges, and Quaternary deposits associated with present streams. Lindgren (1911) estimated that approximately $507 million (at $35.00/oz.) was produced from the Tertiary gravels. Almost all Tertiary gravel deposits can be divided into coarse basal Eocene gravels resting on basement, and overlying upper or "intervolcanic" gravels. While the gravels differ texturally, compositionally, and in gold values, no distinct contact exists between the two. The boundary is usually placed where pebble and cobble beds are succeeded by overlying pebble, sand, and clay beds.

Lower gravels contain most of the gold and rest on eroded bedrock that is usually smooth, grooved, and polished. Where bedrock is granitic, it is characterized by a smooth and polished surface. Where bedrock is slate, phyllite, or similar metamorphic rock, rock cleavage, joints, and fractures acted as natural riffles to trap fine to coarse gold. In many cases, miners would excavate several feet into bedrock to recover the trapped gold. The lower gravels, or "blue lead," of the early miners are well-cemented and characterized by cobbles to boulders of bluish gray - black slates and phyllites, weathered igneous rocks and quartz. Boulders may range upwards of 10 feet in diameter. In many deposits, disseminated pyrite and pyritic pebble coatings are common in the lower blue lead gravels. Adjacent to the bedrock channels, broad gently sloping benches received shallow but extensive accumulations of auriferous overbank gravels sometimes 1-2 miles wide.

The lower unit is also compositionally immature relative to the upper gravel unit as evidenced by their heavy mineral suites. Chlorite, amphibole, and epidote are common constituents in the basal gravels, but are conspicuously absent in upper gravels.

The upper gravels compose the bulk of most deposits, with a maximum measured thickness of 400 feet in the North Columbia District. These gravels carry much lower gold values (rarely more than a few cents per cubic yard) than the deeper sands and are often barren. Upper gravels are finer grained, with clasts seldom larger than cobble size, and contain abundant silt and clay interbeds. Cross-bedding and cut-and-fill sedimentary structures are abundant as well as pronounced bedding and relatively fair to good sorting. Compositionally they are much more mature, with quartz prevailing, and more stable heavy mineral components consisting almost exclusively of zircon, illmenite, and magnetite. Oxidation is common and often imparts a reddish hue to the gravels.

During the Cretaceous, the Sierra Nevada was eroded and its sediments transported westward by river systems to a Cretaceous marine basin. By the Eocene, low gradients and a high sediment load allowed the valleys to accumulate thick gravel deposits as the drainages meandered over flood plains up to several miles wide developed on the bedrock surface. The major rivers were similar in location, direction of flow, and drainage area to the modern Yuba, American, Mokelumne, Calaveras, Stanislaus, and Tuolumne Rivers. Their auriferous gravels deposits are scattered throughout a belt 40 - 50 miles wide and 150 miles long from Plumas County to Tuolumne County. In the northern counties, continuous lengths of the channels can be traced for as much as 10 miles with interpolated lengths of over 30 miles. The ancient Yuba River was the largest and trended southwest from headwaters in Plumas County. Its gravels are responsible for the placer deposits in the North Bloomfield, San Juan Ridge/North Columbia, Moore's Flat, and French Corral districts. Tributaries to the ancestral Yuba River were responsible for most of the other auriferous gravels in Nevada County.
Bedrock erosion degraded the rich gold-bearing veins and auriferous schists and slates as the rivers crossed the metamorphic belts of the Sierra Nevada. Upstream of the gold belts on the granitic Sierra Nevada batholith, channels are largely barren, but become progressively richer as they cross the metamorphic belt and the Mother Lode trend. They become especially enriched after crossing the gold-bearing "serpentine belt" (Feather River Peridotite Belt) upstream of many Tertiary placer districts. While the most gold is contained in the lower sand and gravel, the majority of rich material is within only a few feet of bedrock. Generally, in drift mines only these lower gravels were exploited; however, in hydraulic mines the whole gravel bed was washed. Lindgren (1911) estimated that on average, the hydraulic washing of thick gravel banks up to 300 feet, including both basal and upper gravels, yielded approximately $0.10 to $0.40/yard. Upper gravels alone might average $0.02 to $0.10/yard and lower gavels from $0.50 to $15/yard or more.

The bulk of the gold in the deposits was derived from gold-bearing quartz veins within the low-grade metamorphic rocks of the Sierra Nevada. Gravels that have the highest gold values contain abundant white quartz vein detritus and clasts of blue-gray siliceous phyllite and slate common to the gold-quartz vein-bearing bedrock of the region. Unusually high gold concentrations have also been documented immediately downstream of eroded qold quartz veins exposed in the scoured bedrock.

Most of the gold found in the gravels of the North Bloomfield and Moore's Flat districts is thought to have originated from the famous lode veins of the Alleghany Mining District. The veins in the Nevada City and Grass Valley districts have been proposed as possible sources for the gold in the gravels of the Sailor Flat and Blue Tent diggings.

Gold particles tend to be flat or rounded, shiny and rough, and range from fine and coarse gold to nuggets of 100 or more ounces. Large nuggets were especially prevalent in the Alleghany, North Columbia, Downieville, and Sierra City Districts. The gold particles are almost everywhere associated with black sands composed of magnetite, ilmenite, chromite, zircon, garnet, pyrite, and in some places platinum. Fine flour gold is not abundant in any of the Tertiary gravels. Lindgren (1911) and others have suggested that most of the flour gold was swept westward to be deposited in the thick sediments of the Great Valley.

Valley Springs Formation

After deposition of the Eocene channel gravels, Oligocene-Miocene volcanic activity in the upper Sierra Nevada radically changed drainage patterns and sedimentation. The first of many eruptive rhyolite flows filled the depressions of most river courses covering the Eocene gravels and diverting the rivers. Many tributaries were dammed, but they eventually breached the barriers and carved their own channels within the rhyolite fill. Ensuing intermittent volcanism caused recurrent rhyolite flows to fill and refill the younger channels resulting in a thick sequence of intercalated intervolcanic channel gravels and volcanic flows. In the Scotts Flat District, very little of the Valley Springs Formation remains, having been lost to erosion.

Mehrten Formation

Volcanism continued through the Oligocene to the Pliocene, with a change from rhyolitic to andesitic composition and a successively greater number of flows. During the Miocene and Pliocene, volcanism was so extensive that thick beds of andesitic tuffs and mudflows of the Mehrten Formation blanketed the Valley Springs. Thicknesses ranged from a few hundred to a few thousand feet. Pleistocene erosion removed much of these deposits, but remnants cap the axes of many existing ridges at mid-elevations.
Continued uplift during the Pliocene-early Pleistocene increased gradients allowing the modern drainages to cut through the volcanic mantle and auriferous gravel deposits and deeply into basement. The once-buried Tertiary river gravels were left exposed in outcrops high on the flanks of the modern drainage divides.

Structure

Most Upper Jurassic and younger basement rocks of the northern Sierra Nevada were metamorphosed and deformed during the Jurassic-Cretaceous Nevadan Orogeny. The dominant northwest-trending structural grain is a result of this period of compressive deformation, which produced thrust faults, major northwest-trending folds, and regional greenschist facies metamorphism. This episode also resulted in intrusions of granitic plutons that formed the Sierra Nevada.

Nevadan deformation structures within and between the northern Sierra Nevada lithotectonic blocks are steeply dipping northwesterly trending faults and northwesterly trending folds. These features are best developed in the Eastern, Central, and Feather River Peridotite Belts, where the faults have been collectively described as the "Foothills Fault System" (Clark, 1960). Where the attitude can be determined, most of the bounding faults dip steeply east and display reverse displacement.

The regional northwest-trending structural grain is also at approximately right angles to the prevailing direction of stream flow of both the ancient and modern channels. This grain, expressed in the form of foliation and cleavage in the metamorphic bedrock, served as a good trapping mechanism for the gold particles.

GEOLOGY OF THE LOWELL HILL DISTRICT

Within the district, the Feather River Peridotite Belt narrows to less than a mile wide. Consequently, basement rocks consist of Calaveras Complex rocks to the west, ultramafic rocks and serpentinites of the Feather River Peridotite Belt, and slates of the Shoo Fly Complex of the Eastern Belt to the east, A large part of the district is overlain by volcanic rocks of the Valley Springs and Mehrten formations.

Basal Eocene Auriferous Gravels

The Lowell Hill District contains several separate placer deposits at Lowell Hill, Liberty Hill, Negro Jack Hill, and Remington Hill. By far, the most extensive of these workings are those at Lowell Hill where the auriferous gravels are exposed.

The channel gravels in this district were deposited by a small tributary that drained into a larger tributary of the ancestral Yuba River. This tributary flowed southwestward from the Remington Hill area to join the main tributary at Dutch Flat. The main tributary then flowed generally north-northwestward and deposited the placer gravels in the Dutch Flat, You Bet-Red Dog, Scotts Flat, and Blue Tent districts before joining the ancestral Yuba River in the North Columbia District.

Consistent with the Tertiary gravel deposits in neighboring districts, the deposits can be divided lithologically and texturally into lower and upper units. The thickness of the combined units at Liberty Hill is only 60 feet and equally divided between the two units. The lower unit, or blue lead of the early miners, rests directly on bedrock and contains the richest ores. Lower gravels are well-cemented, quartz-rich, and contain abundant gabbro and serpentinite boulders reflecting erosion of the ultramafic rocks of the Feather River Peridotite Belt bedrock. Lower gravels have been reported to yield between $0.18 and $1.43 per cubic yard.

In most of the workings, the upper unit gravels form the bulk of the deposits. This unit's thickness varies widely. Upper gravels are quartz-rich and much finer, with clasts seldom larger than pebble size and locally including interbeds of clay. Large-scale cross-bedding and cut-and-fill features are common. The upper gravels are considerably leaner than lower gravels, with a reported average yield of $0.24 ($35.00 gold) being reported at Liberty Hill.
The gravel deposits at Lowell Hill are overlain by a 30 foot layer of light colored clay.

Economic information about the deposit and operations

Operation type	Surface-Underground
Development status	Past Producer
Commodity type	Metallic
Significant	Yes
Discovery year	1850

Mining district

District name	Lowell Hill District

Land status

Ownership category	Private
Area name	Nevada County Planning Department
Ownership category	National Forest
Area name	Tahoe National Forest (U.S. Forest Service)

Ownership information

Type Owner

Owner U.S. Forest Service

Type	Owner
Owner	U.S. Forest Service

Comments on the workings information

Hydraulic Mining

Hydraulic mining methods were first applied in 1852 to the Yankee Jims gravels in the Forest Hill District of central Placer County. Its use and methods quickly evolved to where it was applied to most exposed Tertiary gravel deposits. Hydraulic mining involved directing a powerful stream of high pressure water through large nozzles (called "monitors") at the base of a gravel bank, undercutting it and allowing it to collapse. The loosened gravels were then washed through sluice boxes. The remaining tailings were indiscriminately dumped in the nearest available stream or river. Large banks of low-yield gravel could be economically mined this way. In some cases, adits were driven into the exposed face and loaded with explosives to help break down the exposure. One of hydraulic mining's highest costs was in the ditches, flumes, and reservoirs needed to supply sufficient volumes of water at high pressure. A mine might have many miles of ditches as well as dams and reservoirs, flumes, and tunnels. Hydraulic mining flourished for about 30 years until the mid-1880s when the Sawyer Decision essentially brought it to a halt.

Drift Mining

While limited mining of the Tertiary channel gravels by means of shafts and adits commenced soon after their discovery, underground mining flourished after the Sawyer Decision. Drift mining involved driving adits and tunnels along or close to the lowest point in the bedrock trough of an ancient channel and following it upstream along the bedrock surface. Some deeply buried drift mines were originally accessed through vertical shafts requiring timbering, headframes, hoisting, and pumping equipment. Larger shafts were seldom over 3 compartments Smaller mines often had single compartment shafts as small as 2 x 5 feet. Since considerable water was associated with the gravels, it was a serious problem in deeper shafts and costly pumping was required. By the 1890s, due to drainage problems and the expense of hoisting, most major drift mines were accessed through tramway and drain tunnels driven into bedrock below the channels.

Channels were usually located by gravel exposures on hillsides and terraces. Exposures of upstream and downstream gravels were called "inlets" and "outlets," respectively. Where a ravine or canyon cut into, but not through an old channel, the exposure was called a "breakout."

The preferred method of developing an inlet was to tunnel through bedrock under the channel at such a depth and angle as to break through into the bed of the channel providing natural drainage. The overlying gravels could then be accessed directly through the tunnel or by periodic raises and drifts. Development of an outlet involved following the bedrock channel directly into the hillside, the incline of the bedrock providing natural drainage. The tunnel entrances were usually in or near a ravine or gulch to aid in waste-rock disposal.

Prospecting and developing a breakout was more difficult, since the exposed gravel could be in the basal channel or hundreds of feet up on the edge of the channel, making it impossible to locate a prospect tunnel with any certainty. The surest method of prospecting was to run an incline on the pitch of the bedrock. Another method was to sink a vertical shaft on the presumed channel axis. The former method proved superior since it involved less subjectivity and often uncovered paying bench gravels on edges of the old stream. Once the bed of the channel was located, it was prospected by drifts and cross cuts to ascertain width, direction, grade, and the location, extent, and quality of pay.

Prospecting also included projecting the grade and direction of existing channel segments for distances up to several miles. Thus having determined a potential location, a prospect adit or shaft was driven to evaluate it. This was a common method of finding old channels where there were no surface exposures.
Access tunnels were driven in bedrock to minimize timbering and ensure a stable roof, through which upraises were driven to work the placer gravels. Tunnels were generally run under the lowest point of the bed of the channel in order to assure natural drainage and to make it possible to take auriferous gravels out of the mine without having to hoist it.

The main drifts were kept as straight as possible and in the center or lowest depression of the channel. To prospect the width of the channel, crosscuts at right angles to the drift were driven on each side to the rims of the channels or the limit of the paying lead. These were timbered and lagged in soft gravels, but not to the extent of the main drift. In wide pay leads, gangways paralleled the main tunnel to help block out the ore in rectangular blocks. In looser gravels, timbering was required and the main difficulty was preventing caving until timbering was in place. The looser gravels were excavated with pick and shovel. Up until the late 1800s, most workings were driven by hand, then later by machine and pneumatic drills.

Working drifts in the gravel beds and pay leads themselves were larger than the bedrock tunnels and usually timbered due to their extended and long-term use. In wide gravel deposits, as a precaution against caving, gravel pillars from 20 - 40 feet wide were left on each side of the drift. When the main access tunnel was in bedrock following the line of the channel, pillars were not required, as the tunnel in the gravel was only for temporary use in mining the ground between its connections with the bedrock tunnel. Raises to access the gravel were made every 200 - 400 feet as necessary.

The breaking out of gravel (breasting) was done from the working faces of drifts. Usually, 1-2 feet of soft bedrock and 3-4 feet of gravel were mined out to advance the face. When the gravels were well-cemented, blasting was required. Otherwise the material could be removed with picks. Boulder sized material was left underground and only the gravels and fines were removed from the mine.

Bedrock swelling was a frequent problem. Tunnels on and within bedrock were sometimes affected by the upward swelling of the bedrock. In these cases, heavy timbering was required and the tunnel floor had to be periodically cut and lowered to keep the tunnel open.

Soft or fractured slates were the most favorable bedrock. The surface was usually creviced and weathered enough that gold could be found to a depth of 1 foot in the top of the bedrock. Where sufficiently weathered and soft, this upper bedrock layer could be easily removed. If the surface of the bedrock was too hard to be worked, it was cleaned thoroughly, and the crevices and surface were worked with special tools to remove every particle of gold.

According to the gravel's hardness, they were either washed through sluices or crushed in stamp mills. Much of the gravel was so highly cemented it had to be milled several times. Stamp mills with coarse screens were also found to be suitable for milling cemented gravel. For soft and uncemented gravels, a dump, sluices, and water supply under generally low pressure comprised the entire surface workings.

Ventilation of mines was accomplished by direct surface connection through the use of boreholes and the mine shafts and tunnels. It relied on natural drafts, drafts by fire, falling water, or blowers. Within the mines, arrangements of doors were often used to direct the flow of air through the tunnels, drifts, and breasts.

Ore was removed by ore cars of various capacity determined by available power and tunnel size. In smaller mines, small cars were often pushed by hand. In larger mines using horsepower or trains, larger two ton cars could be brought out in trains of 5-10 cars.

Comments on other economic factors

The total production of the district exceeds $1 million, but actual production figures are unknown. Lindgren (1911) estimated that 2 million yards had been removed and that 16 million remained at Liberty Hill. He also estimated that 1.75 million had been removed and 6 million remained at the Remington Hill workings.

Comments on development

The placer deposits in the Lowell Hill District were placer-mined from the mid-1850s through the 1870s, with the Liberty Hill workings being worked again between 1886 and 1915. Hydraulic mining at Lowell Hill was hampered by the heavy overlying beds of clay. Drift mining was done at the Valentine and Swamp Angel mines.

Reference information

Bibliographic references

Deposit

Clark, W.B., 1970, Gold districts of California: California Division of Mines and Geology Bulletin 193, p. 87-88.
Deposit

Lindgren, W., 1900, Colfax Folio: U.S. Geological Survey Atlas of the U.S., Folio 66, 10 p.
Deposit

Lindgren, W., 1911, Tertiary gravels of the Sierra Nevada: U.S. Geological Survey Professional Paper 73, p. 146-147.
Deposit

MacBoyle, E., 1919, Nevada County: Lowell Hill mining district: California State Mining Bureau Report 16, p. 30-33.
Deposit

Saucedo, G. J. and Wagner, D. L., 1992, Geologic map of the Chico Quadrangle: California Division of Mines and Geology Regional Map Series Map No. 7A, scale 1:250,000.
Deposit

Yeend, W.E., 1974, Gold-bearing gravel of the ancestral Yuba River, Sierra Nevada, California: U.S. Geological Survey Professional Paper 772, 44 p.

General comments

Subject category	Comment text
Deposit	The Lowell Hill District contains several separate placer deposits at Lowell Hill, Liberty Hill, Negro Jack Hill, and Remington Hill. By far, the most extensive of these workings are those at Lowell Hill where the auriferous gravels are exposed. The channel gravels in this district were deposited by a small tributary that drained into a larger tributary of the ancestral Yuba River. This tributary flowed southwestward from the Remington Hill area to join the main tributary at Dutch Flat. Consistent with the Tertiary gravel deposits in neighboring districts, the deposits can be divided lithologically and texturally into lower and upper units. The thickness of the combined units at Liberty Hill is only 60 feet and equally divided between the two units. The lower unit, or blue lead of the early miners, rests directly on bedrock and contains the richest ores. Lower gravels are well-cemented, quartz-rich, and contain abundant gabbro and serpentinite boulders reflecting erosion of the ultramafic rocks of the Feather River Peridotite Belt bedrock. In most of the workings, the upper unit gravels form the bulk of the deposits. This unit's thickness varies widely. Upper gravels are quartz-rich and much finer, with clasts seldom larger than pebble size and locally including interbeds of clay. The upper gravels are considerably leaner than the lower gravels.

Subject category

Comment text

Deposit

The Lowell Hill District contains several separate placer deposits at Lowell Hill, Liberty Hill, Negro Jack Hill, and Remington Hill. By far, the most extensive of these workings are those at Lowell Hill where the auriferous gravels are exposed. The channel gravels in this district were deposited by a small tributary that drained into a larger tributary of the ancestral Yuba River. This tributary flowed southwestward from the Remington Hill area to join the main tributary at Dutch Flat.

Consistent with the Tertiary gravel deposits in neighboring districts, the deposits can be divided lithologically and texturally into lower and upper units. The thickness of the combined units at Liberty Hill is only 60 feet and equally divided between the two units. The lower unit, or blue lead of the early miners, rests directly on bedrock and contains the richest ores. Lower gravels are well-cemented, quartz-rich, and contain abundant gabbro and serpentinite boulders reflecting erosion of the ultramafic rocks of the Feather River Peridotite Belt bedrock.

In most of the workings, the upper unit gravels form the bulk of the deposits. This unit's thickness varies widely. Upper gravels are quartz-rich and much finer, with clasts seldom larger than pebble size and locally including interbeds of clay. The upper gravels are considerably leaner than the lower gravels.

Reporter information

Type	Date	Name	Affiliation	Comment
Reporter	10-SEP-2004	Downey, Cameron (Higgins, Chris, T.)	California Geological Survey CGS (Formerly CDMG)
Editor	01-SEP-2007	Schruben, Paul G.	U.S. Geological Survey	Converted from S&A FileMaker format to Oracle. Edit checks on rocks, units, and ages with Geolex search, and other fields.

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